Understanding Isotopic Fractionation

Isotopic fractionation of stable carbon isotopes Carbon-13 (13C) and Carbon-12 (12C) refers to the fluctuation in the carbon isotope ratios as a result of natural biochemical processes as a function of their atomic mass (Taylor, 1987). Variations as such are unrelated to time and natural radioactive decay. It is common practice in radiocarbon laboratories to correct radiocarbon activities for sample fractionation. The resultant ages are termed “normalized”, meaning the measured activity is modified with respect to -25 o/oo (per mille) with respect to VPBD. The correction factor must be added or subtracted from the conventional radiocarbon age.


Beta Analytic’s fees already include δ13C measurements in conjunction with C14 analysis. The lab also provides δ13C measurements NOT in conjunction with C14 analysis except for water samples. Please email the lab for the rates.


Significance of Measuring Isotopic Fractionation

In order to provide radiocarbon determinations that are both accurate and precise, it is necessary to measure the stable isotopes of 13C and 12C and their ratio. This is performed by extracting a small amount of the CO2 generated during the combustion or acid hydrolysis and measuring the 13C/12C ratio relative to the PDB mass-spectrometry standard. This ratio is later used in the calculation of the radiocarbon age and error to correct for isotopic fractionation in nature.

Occurrence and Measurement of Isotopic Fractionation

AMS lab

Fractionation during the geochemical transfer of carbon in nature produces variation in the equilibrium distribution of the isotopes of carbon (12C, 13C and 14C). Craig (1953) first identified that certain biochemical processes alter the equilibrium between the carbon isotopes. Some processes, such as photosynthesis for instance, favors one isotope over another, so after photosynthesis, the isotope C13 is depleted by 1.8% in comparison to its natural ratios in the atmosphere (Harkness, 1979). Conversely the inorganic carbon dissolved in the oceans is generally 0.7% enriched in 13C relative to atmospheric carbon dioxide.

The extent of isotopic fractionation on the 14C/12C ratio (which must be measured accurately) is approximately double that for the measured 13C/12C ratio. If isotopic fractionation occurs in natural processes, a correction can be made by measuring the ratio of the isotope 13C to the isotope 12C in the sample being dated. The ratio is measured using an ordinary mass spectrometer. The isotopic composition of the sample being measured is expressed as δ13C which represents the parts per thousand difference (per mille) between the sample’s carbon 13 content and the content of the international PDB standard carbonate (Keith et al., 1964; Aitken, 1990). A δ13C value, then, represents the per mille (part per thousand) deviation from the PDB standard. PDB refers to the Cretaceous belemnite formation at Peedee in South Carolina, USA. This nomenclature has recently been changed to VPDB (Coplen, 1994).

The δ13C value for a sample can yield important information regarding the environment from which the sample comes or the mixtures of materials used to produce it because the isotope value of the sample reflects the isotopic composition of the immediate environment. In the case of shellfish, for example, marine shells typically possess a δ13C value between -1 and +4 o/oo (per mille), whereas river shells possess a value of between -8 and -12 o/oo (per mille). Thus, in a case where the precise environment of the shell is not known, it is possible to determine the most likely environment by analysis of the δ13C result.

Fractionation also describes variations in the isotopic ratios of carbon brought about by non-natural causes. For example, samples may be fractionated in the laboratory through a variety of means; incomplete conversion of the sample from one stage to another or from one part of the laboratory to another. In Liquid Scintillation Counting, for example, incomplete synthesis of acetylene during lithium carbide preparation may result in a low yield and concurrent fractionation. Similarly, the transfer of gases in a vacuum system may involve fractionation error if the sample gas is not allowed to equilibrate throughout the total volume. Atoms of larger or smaller mass may be favored in such a situation. If, however, the entire sample is converted completely from one form to another (e.g. solid to gas, acetylene to benzene) then no laboratory-induced fractionation will occur.

Conventional radiocarbon ages (BP) and C13/12 Correction

A radiocarbon measurement, termed a conventional radiocarbon age (or CRA) is obtained using a set of parameters outlined by Stuiver and Polach (1977), in the journal Radiocarbon. A time-independent level of C14 activity for the past is assumed in the measurement of a CRA. The activity of this hypothetical level of C14 activity is equal to the activity of the absolute international radiocarbon standard.

The Conventional Radiocarbon Age BP is calculated using the radiocarbon decay equation

t=-8033 ln(Asn/Aon)

Where -8033 represents the mean lifetime of 14C (Stuiver and Polach, 1977). Aon is the activity in counts per minute of the modern standard, Asn is the equivalent cpm for the sample. ‘ln’ represents the natural logarithm.

A CRA embraces the following recommended conventions:

  • a half-life of 5568 years;
  • the use of Oxalic acid I or II as the modern radiocarbon standard;
  • correction for sample isotopic fractionation (δ13C) to a normalized or base value of -25.0 per mille relative to the ratio of δ13C in the carbonate standard VPDB (more on fractionation and δ13C);
  • the use of 1950 AD as 0 BP, i.e. all C14 ages head back in time from 1950;
  • the assumption that all C14 reservoirs have remained constant through time.